Polarforschung 60 (3): 169-180, 1990 (erschienen 1992)

Composition and Paleoenvironmental Implica­tions of Sediments in a Fresh Water Lake and inMarine Basins of Bunger Hills, East Antarctica

By Sergej Verkulieh* and Martin Melles**

Summary: Dara on thc sedimcnt composition from four sediment cores, locatcd in a freshwater lake and in two marine busins of Bunger Hills. EastAntarctica, are presented and discusscd in respcct of thcir paleoenvironmental implications. All investigated sedimcnts arc laruinated. They consistpredominantly of algnc, mosscs and clastics, and exhibit vanous. somctimes vcry high contcnts in carbonatc, organic earbon and sulfur. Thc scdi­ment cornposition is Jargely influenced by the salinity of the watcr, by the degrec of iee coverage, by the supply of mclt watcr, and by thc glaciologi­cal and morphological conditions in the vicinity of thc lakes. Three individual sedimcnt units ean bc distinguished, each probably representing thesame depositiona! time intervals at thc rcspectivc sampling sites. Transitions bctween the units ean be traced back to regional changes in the environ­mental conditions and thercfore providc information conceming the paleoenvironmcntal and paleoclimatical history in thc oasis. Near the Plcisto­cene/Holocenc boundary probably a marine transgression into the oasis occurrcd, resuhing in the Formation of marine busins. Presumably as a conse­quencc of thc postglacial isostatical uplift, parts of the basins were isolated from occan watcr and by meltwater inflow transformcd into fresh waterlakes. Before reaching the recent environmcntal conditions, sampling sites in a large fresh water lake as weil as in a marine inlet have becn uuderanoxic conditions. presumably as a consequenee of a cooler climate than that of today.

Zusammenfassung: Die Zusammensetzung von vier Sedimentkernen aus einem SÜßwassersee und zwei Meeresbecken der Bunger-Oase wird vor­gestellt und in Bezug auf ihre Bedeutung für die Umweltgeschichte diskutiert. Alle untersuchten Sedimente sind laminiert. Sie sind hauptsächlichaus Algen, Moosen und klastischen Partikeln zusammengesetzt und zeigen unterschiedliche, z.T; sehr hohe Gehalte an Karbonat, organischem Koh­lenstoff und Schwefel. Die Sedimentzusammensetzung wird wesentlich vom Salzgehalt des Wassers, vom Grad der Eisbedeckung. vom Eintrag anSchmelzwasser und von den glaziologischen und morphologischen Verhältnissen am Ufer gesteuert. Es lassen sich drei Sedimenteinheiten unterscheiden,die an den einzelnen Probcnnahmcstationen wahrscheinlich jeweils gleiche Ablagerungszeiträume umfassen. Übergänge zwischen den Sedimentein­heiten sind auf Veränderungen der Umweltbedingungen zurückzuführen. Die Sedimentabfolgen liefern daher Informationen Über die Entwicklungder Umweltbedingungen und des Klimas im Bereich der Oase. Nahe der Pleistozän/Holozän-Grenze führte wahrscheinlich eine marine Transgressi­on zur Bildung von Meeresbecken innerhalb der Oase. Als Folge der nacheiszeitlichen isostatischen Landhebung wurden vermutlich Teile der Mee­resbecken vom Ozean isoliert und durch den Eintrag von Schmelzwasser in Süßwasserseen überführt. Bevor die heutigen Umweltbedingungen er­reicht wurden, befanden sich Probennahmestationen in einem großen Süßwassersee und in einem Meeresann unter anoxischcn Bedingungen. Dieswar vermutlich die Folge eines kühleren Klimas als heute.

INTRODUCTION

In order to reeonstruet the climatie and environmental history of Antaretica during Holoeene time, in the lastyears geological investigations on Antaretic lake sediments were increasingly condueted (e.g., WHARTON etal. 1983, TATUR & DEL VALLE 1986, MÄUSBACHERet al. 1989, VOLKMAN et al. 1988, MATTHIES etal. 1990, SCHMIDT et al. 1990, BIRD et al. 1991, BJÖRCK et al. 1991), Because lakes aet as sedimentary basinson the eontinent, lake sediments generally represent more eomplete depositional sequenees than other terrestrialsediments. Furthermore, commonly occurring high organic earbon contents in the lake sediments often enabledetailed age determinations by radioearbon datings. This frequent possibility of obtaining stratigraphie al infor­mation, together with a high sedimentation rate, also often differentiates lake sediments from continental shelfsediments. Hence, the lake sediments probably funetion as the best archives of Holoeene environment al historyin Antarctiea, generally enabling high resolution reconstructions, with good stratigraphie control.

Therefore, geologieal sampling was earried out on lakes and marine basins in the Bunger Hills (Fig. I) duringthe Soviet Antarctie Expedition 1990/1991 (SAE 36). In this study investigations of the sediment eompositionwere made on sediment cores from four sites with distinetly different environmental settings within the oasis.The main purposes of this pilot study are (I) to investigate the influenees of the recent environmental conditionson sediment formation, (2) to detennine the significanee of individual sediment parameters for paleoenviron­mental reeonstructions, (3) to find indications concerning the evolution of the lakes and marine basins, (4) toreconstruet major changes in environmental conditions, and (5), for future sampling, to identify those areas withbest documentations of the Holoeene climatic history in the sediment records.

:;< Sergej Verkulich. Arctic and Antarctic Research Institute (AANI), Bcering Street, 199226 S1. Petersburg, GUS.# Dr. Martin Mellcs, Alfred Wegeuer Institute for Polar and Marine Research, Forschungsstelle Potsdam, Am Telegraphenberg. D-O-1561 Potsdam.FRG.Manuscript rcceived: 24 October 1991. accepted 18 Fcbruary 1992

169

20'

50'

30'

40'

ieeshelf

rock outerops

outlet glaciers

fresh water lakes

oeeanand

~Imarine basins

• i 20'

Oazis/Dobrowolski ~.

(U.S.S.RJPoland) S

Fig. 1: Location of thc Bunger Oasts in East Antarctica and glaciological and hydrographical settings in the surrounding of thc oasts. The encircledbox marks thc loeation of the detailled map of Figure 2.

Abb. 1: Lage der Bunger-Oase in der Ostantarktis mit den glaziologischen und hydrographischen Gegebenheiten der Oasenumgebung. Der umran­dete Kartenausschnitt kennzeichnet die Lage der Detailkarte von Abb. 2.

AREA OF INVESTIGATION

The Bunger Hills (Fig. I) form one of the largest ice-free areas (oasis) ofEast Antarctiea. In the southern part ofthe oasis a large conneeted area of about 280 km' oceurs, exhibiting a high number of fresh water lakes (Fig. 2).To the north numerous islands of altogether about 170 km' are separatcd from the main area by marine basinsand marine inlets. Further to the north the oasis is bordered by the Shackleton !ce Shelf, to the east by the EastAntaretic ice sheet and to the south and west by the Apfel and Edisto glaeiers, respeetively.

The climate in Bunger Hills is mild, relative to other areas of same latitutes in Antarctiea (RUSIN 1961). Theeonditions m'e characterized by a mean annual air temperature of _9.1 0 C, a positive annual radiation balance,and a potential annual evaporation of 450-600 mm/a, which is nearly three times higher than the annual precipi­tation of 200 mm/a.

170

~outlet~ glaciers

fresh waterlakes

18'

16'

14'

12'

1000

10'E55'50'

marinebasins

45'40'35'30'25'

Fig. 2: Detailled rnap of thc Bungcr Oasis with corc locations and geographieal terms mentioncd in thc text.

Abb. 2: Detailkarte der Buttger-Oase mit den Kernpositionen und den im Text erwähnten geographischen Bezeichnungen.

The Bunger Hills show a rugged relief with a maximum elevation of 165 m a.s.l. and maximum water depth inthe fresh water lakes and marine basins of at least 145 m. The main geomorphological features are connected tothe tectonic structures and probably were related before the onset of Antarctic glaciation (BOLSHIYANOV 1990).

During the Weichselian time the Bunger Hills were probably completely covered by ice (BOLSHIYANOV etal. 1990). The deglaciation started near the Pleistocene-Holocene boundary. In early Holocene time the ice hadretreated from most areas of the Bunger Hills. This is evident from the settlement of snow petreis at various pla­ces in the oasis, whose organic deposits were dated by I4C as far back as about 10,000 YBP. Approximately thesame age was detennined by a 14C measurernent on lake sediments, which probably were Iocated a few centi­meters above the bedrock (BOLSHIYANOV & VERKULICH 1991). The ice retreat was followed by a marinetrangression into the oasis, documented in marine tcrraces up to 10 m a.s.l., which contain autochthoneous shellsof marine organisms (VERKULICH 199 I). During the entire Holocene time most parts of the Bunger Oasis re­mained ice-free, however, small-scale variations in the extent of glacier ice and of snow fields are believed tohave taken place.

MATERIAL AND METHODS

The four sediment cores available for this study were collected during the Soviet Antarctic Expedition 1990/1991 (SAE 36) from two marine basins and one lake ofBunger Hills (Fig, 2). Site 6019 is located in the RybiyKhvost Bay (Fig. 2), a typicaI marine bay with only sIightly diluted seawater and a semi-permanent ice cover(KAUP et al. 1990). Izvilistaja Inlet, from which the sediment core of Site 6045 was taken, is part of Transkrip­tii Bay at the western border of the oasis (Fig. 2). The occurence of seawater in the Iower parts of Transkriptii

171

Bay, overlaid by chemically transforrned meltwater, document a connection of the bay with the oeean (KAUPet al. 1990), Transkriptii Bay is described as being perennially ice-covered at least for 30 years (KAUP et al.1990, BOLSHIYANOV et al. 1991), however, we have observed parts of Izvilistaja Inlet ice-free in austral sum­mers. Sites 6082 and 6069 are located in Figurnoe Lake (Fig. 2), a fresh water lake with a semipennanent icecover (KAUP et al, 1990). Major parts of the meltwater from the ice sheet reaching the oasis are flowing throughFigurnoe Lake into Transkriprii Bay. Sites 6082, 6069 and 6045 are situated along this flow path from fresh waterconditions in the east to almost marine conditions in the west.

The cores were taken through the ice cover by gravity corers, having tube diameters of about 3 cm. A steel plateat the top of the tube closes during heaving and thus protects the sediment against washing out. Additionally,due to underpressure in the tube, the plate protects against core loss at the base. The eore recoveries were bet­ween 96 em and 138 crn. After recovery, the sampled eolumns werc stored on fresh air for several hours to ob­tain a higher stability of the sediment, before they were cut into pieces of 5-15 cm length. Ta protect the piecesagainst damage during transportation and against complete drying out during storage, they were wrapped up inparaffin (three cores) or frozen in plastic folios (one core).

The sedimentological analyses were carried out at the Alfred Wegener Institute in Bremerhaven. Primarily, thecores were cut parallel to the core axis into two halves and described in respect to the sediment color (MUN­SELL SOlL COLOR CHARTS 1954) and sediment composition. The sediment structures were described alsodirectly on the sediment corcs, but especially on X-radiographs, which were taken from I cm thick slabs paral­lel to the core axis of the three paraffin packed cores.

In order to quantify the coarse-grained terrigenous content of the bulk scdiment, in the X-radiographs the clasticgrains> 1 mm were counted per centimeter core depth (GROBE 1987). Grain-size distributions were analysedin bulk sediment sampIes of 5-20 cm', which were taken at mean intervals of 10 cm. The samples were oxidizedand disaggregated by means of a 5 % Hp, solution. The contents of the gravel (>2 mm), sand (6311mto 2 mm)and mud fractions «6311m) were determined by wet sieving. The dried coarse fraetions (>6311m) were inspectedin respect of biogenic components using a binocular microscope.

The sulfur, organic carbon and carbonate contents were analysed on a CS-125 Carbon-Sulfur Determinator (LECOCorporation) in mean intervals of 5 em. The total carbon and sulfur contents were measured in freeze-dried andground bulk sediment samples, the organic carbon contents were measured in corresponding samples, whieh havebeen treated with hydrochloric acid to remove the carbonate. The carbonate contents were calculated from thecontents of carbonaceous carbon, the difference between total and organic carbon.

RESULTS

All analysed sediment cores are weil defined laminated. Bioturbation structures due to infaunaI activity do notoccur. The sediments consist mainly ofthree different types of sediment components, which can be easily dis tin­guished: algae, mosses and clastic grains. The individual algallayers have grayish, yellowish and greenish eol­ors and vary in thickness between a few tenths ofmillimeters and about 2 mm. The thicknesses ofthe moss layersrange from 1-7mm. With gray, dark gray, greenish gray, olive gray and blaek their colors are much darker thanthose ofthe algallayers. Terrigenous sediment components may oecur as single dispersed grains, single definedlayers, 01' as coherent multi-Iayered horizons. Their eolors are generally gray and light gray, the thieknesses ofindividuallayers are often much less than I mm.

Site 6082 was sampled in the eastern part of Figurnoe Lake in a water depth of 67 m (Fig. 2). Two distinet unitsean be distinguished in the sediment sequenee (Fig. 3).

Unit I (0-104 cm): The sediment consists predominantly of laminated algal mats. In the algal mats moss bands,increasing in number and thickness downcore, are interbedded. The sedirnent eontains high amounts of clasticgrains >1 mm, possibly exhibiting cyelie fluctuations, However, almost no gravel and relatively low, weaklyvarying sand eontents result in a clear dominance of mud in the grain-size distribution. The earbonate eontentshave a wide range. In contrast, the contents of organic carbon and sulfur are very constant in low values.

172

E lltho- >1 mml gravell sand I mud color.!:O logy 3 cm 3 (%) Munsell Soll

10 0 20 40 60 80 ColorChart 0

carbonate(%)

20 40

organic carbon(%)

4 8 120

sulfur(%)

2 3 4 5

-'e::l

10 0-138cm:

20larnina-

30 tion of

algae40 layers:

5Y5/2,

50 5Y5/1,5YR6/4,

6010YR5/610YR6/4

70 and

80 mosslayers:

905Y4/1,5Y4/2,

5Y2.5/1100

lower

110 part ofcore

120gene-rally

darker130

Legend for Iithology: _ mosses [»>=</ algae k~.;.~.;.~.;.~.;.~ ciastics

Fig. 3: Core log of the scdimentary succession at Sitc 6082 front thc eastern Figumoc Lake.

Abb. 3: Kerndiagramm der Sedimentabfolge an der Station 6082 vom östlichen Figurnoe-Sce.

Unit 2 (104-138 cm) consists of algal mats with distinctly higher amounts of moss bands than in Unit I, especiallyin the upper part. Similar to Unit I the sand content is low, gravel is absent and the carbonate content is in thesame range. Beside the higher moss content, Unit 2 differs from Unit I in lower numbers of clastic grains> Imm and higher contents of organic carbon and sulfur.

The sediment at Site 6069 from the western part ofFigumoe Lake in 56.5 m water depth (Fig. 2) can be subdi­vided into three units (Fig. 4). The first two units show many similarities with those of Site 6082 from theeastern part of Figumoe Lake.

Unit I (0-53 cm): As in Unit I at Site 6082, the sedirnent consists predominantly of laminated algal mats with adowncore increasing interbedding of moss layers. Additional similarities are relatively high contents of clasticgrains> I mm, lack of gravel in the sediments, relatively low sand contents, similar values and high variabilityof the carbonate contents, and relatively low and constant contents in organic carbon and sulfur. Unit I at Site6069 differs from that of Site 6082 by a lower absolute number of moss layers, by lower absolute numbers ofclastic grains >I mm and, less clearly, ofthe sand fraction, and by the much lower thickness, approximately halfof that at Site 6082.

Unit 2 (53-85 cm): Confonnity between the units 2 at sites 6082 and 6069 lies in the high moss content, especiallyin the upper part, distinctly higher than in the corresponding units 1. Similarity in units 2 at both sites addition­ally lies in the lack of gravel, relatively low contents in sand and in clastic grains> I nun, similar values in car­bonate contcnts, and high contents in organic carbon and sulfur, relative to the units 1. Unit 2 at Site 6069 dif­fers from that at Site 6082 by higher absolute contents in moss and sulfur, and by lower absolute numbers ofclastic grains » I mm.

173

E lltho- >1 mml gravell sand 1mud color.!:- logy 3 cm3 (%) Munsell Soll

o 10 0 20 40 60 80 Color Chart

carbonate(%)

20 40

organic carbon(%)

4 8 120

sulfur(%)

2 3 456

-';:~

, , , , ,0-85

10 cm:lamina-

',:. tion of:20

-\ algae:

:'::::.

5GY4/1,30 5Y4/2,

.,' . 5Y4/3,

40.:<: .5YR51

::{:'. andmoss:

50.,:,::,

5GY6/1,.::.:.:.:.2.5YR

60.v 2.5/0,

.5YR51

70sediment

.:<.. in parts

'~"::black:

80 :.>: 1OYR2/1,

90 }~:~~~~}: 85-101:2.5Y6/0,

100 2.5Y5/0

Legend tor Iithology: _ mosses [>',«;1 algae E.;.~.;.~.;.~.;.~.;.j clastics

Fig. 4: Core leg of the scdimeruary succcssion at Sire 6069 frorn the wcstem Figumoe Lake.

Abb. 4: Kerndiagramm der Seclimcntabfolge an der Station 6069 vom westlichen Figurnoe-See.

Unit 3 (85-101 cm): The sediment of Unit 3, separated from Unit 2 by a distinct color change, differs clearlyfrom those of all other units. It consists almost totaIly of terrigenous, finely laminated components of gray andlight gray colors. Algae occur in very low contents in Unit 3 and mosses are completely lacking. The sedimentis highly consolidated. It shows relatively low contents in clastic grains> I mm while having higher sand con­tents than the overlying sediments. Unit 3 sediments are the only ones which are almost free of carbonate, oforganic carbon, and of sulfur. At the base of the column the core tube was nearly fi1ledby a single grain of about2.5 cm diameter, overlain by a few centimeters of coarse sandy to graveIly sediments.

Site 6045 was sampled in 37.5 m water depth in Izvilistaja Inlet (Fig. 2). Although the sediment sequence showsminor differences in composition than the cores from Figurnoe Lake, two different units can be distinguished(Fig.5).

Unit I (0-83 cm): Finely laminated algal material without any moss. The sediment contains high amounts ofclastic grains> I mm and of sand, however, gravel is lacking in the grain-size samples. The carbonate contentsare relatively high, especiaIly in the upper part of Unit I, with a decreasing trend to the lower part. Organic ca­rbon and sulfur show a high constancy over the whole unit and low values in respect to Unit 2 of this site. Theserelatively low values as weIl as the high numbers of clastic grains> I mm are similar to Unit I sediments at sites6082 and 6069 from Figurnoe Lake.

Unit 2 (83-96 cm): As Unit I at this Site 6045, Unit 2 also consists predominantly of algal materiallacking anymoss. The differences between these two units are distinctly lower numbers of clastic grains> I mm and lowercontents in sand in Unit 2. Additionally, in Unit 2 the contents of organic carbon and sulfur are higher than inUnit I. Except the lack of any rnoss, Unit 2 of Site 6045 exhibits several similarities to units 2 of sites 6082 and6069, including the relatively low numbers of c1astic grains> I mm, and the high contents of organic carbon andsulfur.

Site 6019 is located in 88 m water depth in Rybiy Khvost Bay (Fig. 2). The 123 cm thick sediment sequencerecovered ar this site is characterized by a large homogeneity, preventing the distinction of individual sedimentunits (Fig. 6).

174

carbonate(%)

20 40

organic carbon(%)

o 4 8 120

sulfur(%)

2 3 4 5

-'c:l

Legend for lithology: _ mosses (;:;>:;::1 algae t.;.~.;.~.;.~.;.~.;.j c1astics

Fig. 5: Corc log of thc scdimcntary SU<.:CCSS10ll ur SIll' 6045 Irom ihc lzvilistaja lnlct. castern Transkriptii Bay.

Abb. 5: Kerndiagramm der Sedimentabfolge an der Station 6069 vom Izvilistaja- Meeresarm in der östlichen Transkriptii-Bucht.

~E lltho- >1 mml gravell sandI mud color_u 3logy 3 cm (%) Munsell Soil

o 20 40 60 80 Color Ohart 0

carbonate(%)

20 40

organic carbon(%)

4 8 120

sulfur(%)

234

-'c:l

6

··········10 ······ · ··········20 ······ ···········30 ················ · ·40 ······ · "0····· Q)

····· c50 ····· '§·········· *60 ····· "0· · ······ ö· ·70 ····· C

· · ······· ······80 ···············90 ··············100 ················ ·110 ······ ···········120 ······ · ·

, .co----

. , ,

I'~mud§l 0-33 -\ 160191'. crn:

5Y4/1

r.§='J gravel~33-35 ~ , )

.' ern: . ~'.:".. 7.5R4/6

(~ sand E"§3 )0

f 135-123

cm:7.5R2/0

..'.

~

<'.

Legend for Iithology: _ mosses [:-;-:-:-:J algae f~+~~+~+l c1astics

Fig. 6: Core log of thc sedimentary succcssion at Sill' 6019 from thc southcrn Rybiy Khvost Ba)'.

Abb. 6: Kemdiagramm der Sedimentabfolge an der Station 6069 von der südlichen Rybiy-Khvost-Bucht.

175

The sediment smelt strongly of H,S when extruded from the core tube in the field. It consists predorninantly oflaminared algal material, mosses are absent. The contents of the coarse fraction in 6019 are much lower than inthe other three cores mentioned in this study, except two samples in the upper part of the core, which containsignificant amounts of graveI. The values of carbonate, organic carbon, and sulfur are very constant and low inrespect to the sediments frorn the other sites. As the only one core, the coarse fraction of 60 19 contains biogeniccomponents, occurring throughout the core. These components include arenaceous foraminiferal tests of Miliam­mina arenacea, a marine organism. In addition, marine diatoms were found in the mud fraction (Z. PUSHINApers. comm.). The occurrence of a marine fauna in the sediments of Rybiy Khvost Bay was also described byBOLSHIYANOV et al. (1991).

DISCUSSION

Paleoenvironmental significance ofsediment parameters determined

The contents of the main sediment components algae, mosses, and clastics depend on a number of processes.The contents of algae and mosses are influenced by their production in the water column, by their deposition onthe lake floor, by their redistribution due to bottom currents or gravitational transport, by their dilution with othersediment components, and by their bacterial or chernical decomposition. The absence of bioturbation structuresindicates that an influence of a grazing fauna on the algae and moss contents may be negligible.

The thicknesses of the regularly layered algal mats vary between a few tenth of millimeters and about 2 mm.This is within the range of annual sedimentation rates detennined on Antarctic lake sediments from VestfoldHills, about 1,000 km to the west from Bunger Hills (BIRD et al, 1991), as weil as from Livingston Island, inthe Antarctic Peninsula region (BJÖRCK et al. 1991). This indicates that each individual Iayer may represent anannual deposition, possibly due to aspring or sumrner algal bloom. In contrast, the moss layers are less regular­Iy distributed in the sequences and exhibit more variable thicknesses. Their occurence therefore might representenvironmental conditions more independent from the annual cycle. In Bunger Hills the moss layers were sampledonly in the sediment cores from the fresh water Burevestnik Lake (BOLSHIYANOV et aI. 1991) and FigumoeLake (sites 6069 and 6082). Mosses were described from other regions of Antarctica also exclusively frorn freshwatcr lakes, e.g., from Schinnacher Oasis (INGOLE & PARULEKAR 1990, MELLES in press), Livingston Island(BJÖRCK et aI. 1991) and King George Island (MATTHIES et aI. 1990). This indicates that salinity is a limi­ting factor for moss growth.

The clastic sediment components may have different sources and transport mechanisms, Glaciers or the ice sheet,when reaching the lake, may supply poorly sorted clastic material, containing all grain-size fractions, fromlarge distances directly in the lake water or on the lake ice cover. Similar poorly sorted debris, but from a localsource, may be delivered by gravitational transport downslope adjoining hills. Material of much better sorting,and with limited maximal grain sizes, could be carried out into the lakes by meltwater inflow streams and, probablyin a lesser amount, by eolian transport.

The grain-size distribution shows a clear dominance of the mud fraction in all investigated sediments. This indi­cates that during the time span represented by the sediments the current velocities at the bottoms of the lakesand marine basins were not strong enough at least for transporting sand, i.e, they were lower than about 3 cm/sec (SINGER & ANDERSON 1984). The almost exclusively terrigenous sand fraction as well as the fraction> I mm, whose grain numbers were detennined per centimeter core depth at three sites, are irregularly distribu­ted in the sediments or concentrated in thin layers. The low thickness of the layers and the lack of graded bed­ding makes their deposition by gravitational transpült events, such as turbidity currents, slumps or slides, un­likely. More likely, therefore, is their supply by lake ice or icebergs, either by downward transport through theice cover as described by SQUYRES et aI. (1991) or by melting of the ice in austral sumrner. The degree of thecoarse-grained material in the sediments is not necessarily related to the supply of coarse-grained material intothe lake, but also to the dilution by biogenic components, as weil as enrichment or diminishing with fine­grained biogenic or clastic material as a result of currents.

176

The carbonate contents in the investigated sediments generally are high, except in Unit 3 at Site 6069, wherecarbonate is almost lacking. In spite of the high carbonate values microscopical examinations of the coarsefractions did not reveal carbonate components, neither biogenic nor terrigenic, proving a major carbonate occur­rence in the rnud fraction. The carbonate probably is the result of precipitation of carbonate rninerals, a processwhich has been widely reported in Antarctic lakes (BURTON 1981, WHARTON et al. 1982, 1983; BlRD et al.1991). Carbonate dissolution at least today is negligible because the water in all lakes of Bunger Oasis exhibitalmost neutral or slightly alkaline reaction (KAUP et al. 1990). Because variations in the carbonate profilesgenerally do not correlate with other sediment parametcrs, the carbonate precipitation is probably largely inde­pendent from the large-scale environmental conditions. Therefore the carbonate contents in the lake sedimentsare difficult to interpret in respect to paleoenvironmental reconstructions.

The contents of organic carbon and sulfur in the investigated sediments generally show a similar distributionpattern. Their contents are influenced for example by the biogenic production in the water column, which de­pends mainly on the availibility of nutrients and of light. Another factor influencing the organic carbon and sul­fur contents is the biological or chemical decomposition in the water column or after deposition in the sediment.In addition, the contents of organic carbon and sulfur are influenced by their redistribution due to currents andgravitational sediment transport, and by the degree of dilution with other sediment components.

Paleoenvironmental rcconstructions by the lake sediment composition

The sediment units (1,2, and 3), distinguished in the four investigated sediment cores, have a number of similaritiesin sediment composition, respectively. Because the composition of the sediment is directly dependent on theregional environmental conditions, the individual units probably are comparable at the different sites and repre­sent same time intervals of deposition. The interpretation of the individual units therefore provides informationsconceming the environmental history in and around the lakes and marine basins of Bunger Hills.

Unit I, sampled at all four sites, inc1udes the surface sediments and therefore represents environmental condi­tions similar to those oftoday. Unit I in eastern Figumoe Lake (Site 6082) differs from that in western FigurnoeLake (Site 6069) in higher sand contents, in lower moss contents and in an almost twice as high sedimentationrate (Figs. 3 and 4). The higher sand content at Site 6082 could be due to higher current velocities in the watercolumn, causing an enrichment of the coarse fraction by diminishing of fine material. However, sediment dimin­ishing at Site 6082 is unlikely because of the distinctly higher sedimentation rate. More likely, therefore, is en­hanced sand supply by lake ice or icebergs at Site 6082 as a result of the higher proximity to the ice sheet. Thishigher terngcnous sand supply alone cannot explain the doubled sedimentation rate at Site 6082, relative to Site6069. The higher rate of sedimentation is probably additionally the result of a distinctly higher algae accumula­tion at Site 6082 in eastem Figumoe Lake, because the moss content there is even lower and the carbonate con­tents are in the same range at both sites. This suggestion is supported by measurements of nutrient inflows withglacial meltwater into Dalekoye Lake (Fig. 2), which are connected with high biogenic production (KAUP et al.1990). The lower moss content at Site 6082 is not necessarily the result of a lower production, but rather of dilu­tion by algal and c1astic material.

At Site 6045 from Izvilistaja Inlet, eastern Transkriptii Bay, as weil as at Site 6019 from Rhybiy Khvost BayUnit 1 does not contain any mosses due to the high salinities of the water in these marine basins (Figs. 5 and 6).In spite of the lack of mosses, the thickness of Unit I at Site 6045 again is higher than at Site 6069 from westernFigurnoe Lake (Fig. 4). This higher sedimentation rate could be the result of higher accumulation of algae, be­cause the nutrient concentrations in Transkriptii Bay are significantly higher than those in Figumoe Lake (KAUPet al. 1990). However. the existence of an almost perennial ice cover on Izvilistaja Inlet could have limited al­gae production by reducing light penetration into the water. Hence, the most probable explanation for the highersedimentation rates at Site 6045, relative to Site 6069, is a higher terrigenous sediment supply, which could bedocumented in distinctly higher sand contents at Site 6045 (Fig. 5). The high sand content cannot be due to di­minishing of fine material as a result of higher current velocities in Transkriptii Bay, because below 88 m waterdepth (weil below Site 6045) a stagnant water body with high contents of H,S and phosphates occurs (KAUP etal. 1990), indicating only very weak circulation. In the uppermost sediment centimeters of Unit I at Site 6045the carbonate and organic carbon contents increase. In these sediments the first occurence of fresh water dia­toms is observed (Z. PUSHINA pers. comm.), indicating an increase of rneltwater input into Izvilistaja Inlet duringthe last decades or centuries.

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In the recovered sediments from Site 6019 in Rybiy Khvost Bay (Fig. 2) no significant changes in the sedimentparameters occur (Fig. 6), including the continuous presence of marine organisms. Hence, the whole sedimentseguence represents environmental conditions similar to those of today, and the sediments were deposited probablywithin the time interval of Unit I. This rneans, that the sedimentation rate in Unit I at Site 6019 presumably ismuch higher than at all other sites investigated in this study. The high sedimentation rate could only be due to avery high algae accumularion, because the sand and carbonate contents are low and mosses are absent. A highalgae production is expected, because the nutrient concentration in Rybiy Khvost Bay waters is very high and,different to Transkriptii Bay, the ice cover is only semipermanent (KAUP et al. 1990).

Unit 2 sedimenrs were recovered in the cores from sites 6082 and 6069 from Figu1110e Lake and Site 6045 fromIzvilistaja Inlet (Fig. 2). At all of these sites units 2 differ from units I in higher organic carbon and sulfur con­tents, and in lower contents of coarse-grained material (Figs. 3-5). Additionally, at the two sites from the freshwater Figurnoe Lake the moss contents in Unit 2 are higher than in Unit I.

According to BIRD et al. (1991) the distinctly higher organic carbon and sulfur contents in Unit 2 sediments,relative to Unit I, are interpreted as representing a situation with lack of organic carbon oxidation and occur­rence of bacterial sulfate-rcduction. These anoxic conditions probably existed during the deposition of Unit 2 inthe water depths of the investigated sites of both the Figurnoe Lake and the Izvilistaja Inlet. Anoxie conditionscould be the result of a very high organic flux to the bottom or of only weak water circulation which may resultin limited mixing of the water column. A high organic accumulation could be demonstrated by the higher mosscontents in Unit 2, relative to Unit I, however, this also could be an effect of lower accumulation rates in Unit2. In contrast, a weaker water circulation in Unit 2 than in Unit I could clearly be documented in lower contentsof coarse-grained sediment cornponents, promoting the settlement of large amounts offine material. Lower currentvelocities could be due to less meltwater supply as weil as to a more permanent ice coverage, reducing windinduced water movements - both of these processes would indicate cooler climatic conditions than those of to­day.

Similar to Unit I, Unit 2 at Site 6082 (eastern Figurnoe Lake) differs from that of Site 6069 (western FigurnoeLake) in lower moss contents, in higher sand contents and in a higher sedimentation rate (Figs, 3 and 4). Thesedifferences are again interpreted as being the result of a higher accumulation of algae and terrigenous materialin eastern Figurnoe Lake, which results in relatively lower moss contents. In contrast to Figurnoe Lake, Unit 2at Site 6045 from Izvilistaja Inlet, eguivalent to Unit 1, lacks mosses and contains marine diatoms. The simila­rities in the regional differences within units land 2 indicate that the large-scale paleogeographical situationwas relatively constant and that the transition from Unit I to Unit 2 represents changes in the climatic conditi­ons rather than changes in the geographical situation.

Unit 3 sediments were recovered exclusively at Site 6069 from western Figumoe Lake (Fig. 2), where they occurat the base of the sediment seguence (Fig. 4). It is the only unit, which consists predominantly of terrigenoussediment components. Additionally, in Figurnoe Lake Unit 3 is the only unit lacking any mosses, indicating amarine origin of Unit 3 sediments. This suggestion is supported by the occurence of a marine neritic diatom as­semblage in similar highly terrigenous sediments at the bases of sediment cores from both Burevestnik Lake(BOLSHIYANOV et al. 1991, Fig. 2) and Figurnoe Lake (Z. PUSHINA pers. comm.). Radiocarbon datings onoverlaying algal sediments from these lakes (BOLSHIYANOV et al. 1991) indicate an age of >9,000 y BP forthe terrigenous sediments.

The very low content of biogenic components in Unit 3 could be the result of a thick, perenniallake ice cover,possibly additionally covered by snow, which could have limited biogenic production due to reduced lightpenetration into the water column. However, this is unlikely, because recently in Izvilistaja Inlet a high accu­mulation of algae occurs, documented in the surface sediment at Site 6045 (Fig. 5), although the inlet is almostperennially ice-covered. More likely, therefore, is a covering by floating glacier ice, preventing light penetra­tion and significant biogenic production in the water column. The tenigenous material could have been suppliedinto the water by melting of the ice. Subsequently, marine currents or melt water streams of varying velocitiescould have resulted in sorting and stratification of the deposited material. The fining upward within Unit 3 couldbe due to increasing distances from the terrigenous source.

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Hence, it is probable that the sediments of Unit 3 represent the initial lake stage, joint with a marine transgres­sion, which possibly caused the floating of ice masses in the area of Bunger Hills. A transgression onto the oasisis also deduced from marine terraces, today located up to 10 01 a.s.l., by VERKULICH (1991). And marine con­ditions in early Holocene times were also reconstructed for lakes from Vestfold Hills (PICKARD et al. 1986,BIRD et al. 1991). The border between units 3 and 2 in Figurnoe Lake corresponds with the transition frorn ma­rine to lacustrine conditions. This could be a result of postglacial isostatical uplift in this region, cutting the wa­ter path between the lake and the acean.

CONCLUSION

Based on the experience from this pilot study the following conclusions can be drawn concerning sedimentolo­gical work on sediments from fresh water lakes and marine basins in the Bunger Hills.

(I) No indication for erosional processes was found in the sediment record. Hence, at least parts of FigurnoeLake, Transkriptii Bay and Rybiy Khvost Bay existed during the entire depositional time of the investigatedsedirnents.

(2) The fresh water Figurnoe Lake probably originates from a marine inlet which was formed by a marine trans­gression during latest Pleistocene or earliest Holocene time (Unit 3). Later, the inlet became isolated fromocean water, presumably due to the postglacial isostatical uplift, and meltwater gradually replaced the originalseawater (Unit 2).

(3) During a considerable time span within the Holocene (Unit 2) at least parts of Figurnoe Lake and IzvilistajaInlet met anoxic conditions, which presumably can be traced back to a cooler climate than that of today. In morerecent times (Unit I) all core locations exhibit oxic conditions.

(4) All sediment parameters determined in this study, except carbonate content, exhibit significant variations withinthe cores and probably reflect the regional environmental conditions. The determination of sediment color, com­position, structure, grain-size distribution, organic carbon content and sulfur content therefore can be used forpaleoenvironmental interpretation and reconstruction. .

(5) Sediment cores from the marine basins differ from those from fresh water lakes by higher sedimentationrates. Hence, the marine sedirnents expect a higher resolution of the environmental changes. In contrast, lakus­trin sediments of same length comprise a longer time period. Additionally, they expect a better stratigraphy dueto often higher organic carbon content.

(6) For future work, the frequently occuring high content of organic carbon, carbonate, sulfur, and algae in thesediments will enable the determination of additional parameters for a more detailled reconstruction of theHolocene environmental conditions in the Bunger Hills area. These parameters include radiocarbon dating, meas­urements of stable carbon, oxygen and sulfur isotopes as well as micropaleontological investigations.

ACKNOWLEDGMENT

We thank the collegues on the Soviet Antarctic Expedition 1990/1991 (SAE 36) for their help during field work.Prof. Dr. Füttcrer (AWI) and Prof. Dr, Klokov (AANI) are gratefully acknowledged for enabling our joint labo­ratory work in Bremerhaven. Z. Pushina is thanked for providing unpublished results from diatom analysis, Weare also indebted to Dr, R. Mäusbacher for a critical and helpful review of the manuscript and to Dr, G. Kuhnfor fruitfull discussions. This is contribution No. 530 of the Alfred Wegener Institute for Polar and Marine Re­search, Bremerhaven.

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